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  <div class="section" id="seawater-cp">
<h1>seawater.cp<a class="headerlink" href="#seawater-cp" title="Permalink to this headline">¶</a></h1>
<dl class="function">
<dt id="seawater.cp">
<code class="sig-prename descclassname">seawater.</code><code class="sig-name descname">cp</code><span class="sig-paren">(</span><span class="sig-paren">)</span><a class="reference internal" href="../../_modules/seawater.html#cp"><span class="viewcode-link">[source]</span></a><a class="headerlink" href="#seawater.cp" title="Permalink to this definition">¶</a></dt>
<dd><p>Compute the heat capacity of seawater at fixed conditions</p>
<p>Per Figure 5 in Sharqawy et al. (2010), the heat capacity of seawater 
only varies +/- 5 percent over practical temperatures and salinities 
for deepwater blowouts.  If we let heat capacity depend on temperature
and or salinity, computing the temperature of water given the total 
heat becomes an implicit calculation.  This is a problem for the plume
models.  As a result, we choose to set the heat capacity to that of
seawater at 10 deg C and 34.5 psu.</p>
<dl class="field-list simple">
<dt class="field-odd">Returns</dt>
<dd class="field-odd"><dl class="simple">
<dt><strong>cp</strong><span class="classifier">float</span></dt><dd><p>heat capacity of seawater (J/(kg K))</p>
</dd>
</dl>
</dd>
</dl>
<p class="rubric">Notes</p>
<p>This approximation is valid since we have treated cp to be a constant in
derivation of the governing equations.  If we let cp vary with T and S, 
then the governing equations will contain a lot of new terms coming from
gradients of cp due to spatial variation of T and S.  This complexity is
unnecessary due to the small variation of cp over the environmental 
range.  In addition, the temperature T will become an implicit equation
of the heat, H, since H = rho(T) cp(T) T.  Note that we have also used
the reference density to define rho in the relation for heat:  rho(T) -&gt; 
rho_0.  This is known as the Boussinesq approximation.</p>
</dd></dl>

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